Preliminary Arlindo Results from MAK-1
and MAK-2.

Makassar Strait is the primary pathway of the
Pacific to Indian Ocean transport referred to as the Indonesian
throughflow. The transport through Makassar Strait was measured
as part of the Indonesian-USA Arlindo program, at two moorings
deployed within the Labani Channel, a deep (2000 m) constriction
(45 km) near 3°S (Fig. 1). Both moorings
were operative from December 1996 to February 1998, a 1.4 year
time series, when the MAK-2 mooring was released and recovered;
the MAK-1 mooring was recovered in early July providing a 1.7
year record. The MAK moorings were deployed during a weak La Niña
phase. An El Niño condition began in March 1997, becoming
extreme during 1997 summer and fall, relaxing in early 1998. Arlindo
data will be the subject of much study by the Arlindo research
team**, but because of WOCE interest in Indonesian Throughflow
we offer this preview of Makassar transport based on the Aanderaa
current meters (current, temperature, pressure) and temperature-pressure
pods of MAK-1 and MAK-2.
The Indonesian maritime continent with its complex network of
passages and basins connecting the Pacific and Indian Oceans inhibits
free communication between the Pacific and Indian Oceans. Schneider
(1998) using a couple model, shows that the presence of the Pacific
to Indian interocean transfer shifts the warmest SST and associated
atmospheric convective region towards the west, relative to a
no throughflow condition. Webster et al. (1998) state: the Indonesian
throughflow heat flux "...is comparable to the net surface
flux over the northern Indian Ocean and a substantial fraction
of the heat flux into the western Pacific warm pool...it would
appear that the throughflow is an integral part of the heat balances
of both the Pacific and Indian Oceans."
Observations indicate that the throughflow is composed mostly
of North Pacific thermocline and intermediate water flowing through
Makassar Strait (Gordon and Fine, 1996), which then passes into
the Indian Ocean through the passages of Lesser Sunda Islands.
East of Sulawesi South Pacific water infiltrates the lower thermocline
and dominates the deeper layers, including the Lifamatola Passage
overflow into the deep Banda Sea (Van Aken et al., 1988; Gordon
and Fine, 1996; Hautala et al. 1996), but it is unlikely that
the eastern channels carry total more than 3 Sv.
Indonesian throughflow estimates based on observations, models
and conjecture range from near zero to 30 Sv (Godfrey, 1996).
Measurements in the Lombok Strait in 1985 (Murray and Arief, 1988;
a near zero SOI value) indicate an average transport of 1.7 Sv.
Molcard et al. (1996) as part of the French-Indonesian program
JADE, find a mean transport to the Indian Ocean of 4.3 Sv between
the sea surface and 1250 m in the Timor Passage from March 1992
to April 1993 (an El Niño period). With the Lombok values
the JADE results suggest 6 Sv transport through the Lesser Sunda
Islands. An annual mean throughflow of 5 Sv is estimated from
XBT data for the upper 400 meters between Java and Australia for
the period 1983 to 1989 (Meyers, 1996). T.H. Aung presented the
results of the 1993-94 (El Niño period) ASEAN current meter
array in the Makassar Strait at a June 1995 meeting in Lombok.
The three ASEAN moorings were deployed in the wide northern entrance
to Makassar Strait. Most of the current meters were below 400
m with one instrument at 275 m, thus missing the main thermocline,
making estimation of transport difficult, but Aung states that
the Makassar transport may be as large as 11 Sv. Potemra et al
(1997) model study and inspection of TOPEX/POSEIDON data find
a summer maximum of 11 Sv, and a winter minimum of 4 Sv, with
a 7.4 Sv 9-year mean. Gordon et al. (1997) find on average 9 Sv
of Indonesian throughflow water advected westward within the Indian
Ocean.
The preliminary findings of the Arlindo Makassar MAK-1 and MAK-2
data are presented in Figs 2 , 3
and 4, some key points each of which will
be explored in detail by the Arlindo team, are:
1. The Makassar thermocline depth and transport reflect the phases
of ENSO, with an ambiguous seasonal cycle: deeper thermocline,
larger throughflow during La Niña; shoal thermocline, with
reduced transport during El Niño. Additionally, during
the El Niño months December 1997 to February 1998 the transport
average is 5 Sv, while during the La Niña months of December
1996 to February 1997 the average is 12 Sv, a 2.5 fold difference.
2. Along channel flow exhibits much activity at frequencies above
seasonal. A special event occurs in May and June 1997 when a marked
relaxation of the throughflow transport is recorded. Candidates
responsible are: Pacific Ocean Rossby waves, Indian Ocean coastal
Kelvin waves, local atmosphere and dynamics internal to the Indonesian
Seas.
3. The Makassar Strait 1997 twelve month average throughflow is
9.3 Sv. This assumes that the flow above the shallowest Aanderaa
equals the flow at that current meter (case B, Fig.
4). Other models for the surface flow yield 1997 transport
average of 6.7 Sv (zero surface flow, case C, Fig.
4) to 11.3 Sv (thermocline shear is extrapolated to the sea
surface, case A, Fig. 4). How to handle
the water flow above the shallowest Aanderaa current meter is
an important issue, not just for the mass transport but also for
the interocean heat and freshwater flux and for monitoring array
design. We will have a firmer idea of the surface layer flow when
the moored ADCP data are processed. The MAK-2 ADCP has a record
from 1 December 1996 to 9 March 1997 before it flooded; the MAK-1
ADCP data record will be processed later this year. The preliminary
MAK-2 ADCP data show a maximum of along channel flow at 110 m,
with near zero surface flow. The hull ADCP of the Baruna Jaya
IV, the Indonesian research vessel used in the Nov/Dec 1996 deployment
and Feb 1998 recovery of the MAK moorings reveal similar reduction
of along channel speed in the surface layer. The MAK-1 monthly
along channel speeds displays higher southward values at the 250
m instrument relative to the 200 m instrument for 13 of the 20
month record (the months with higher transport). The data suggests
shear reversal between 200 and 250 m in the western Labani channel,
closer to 100 m in the east.
4. The Makassar transport (case B) determined from the Arlindo
data is at the higher end of estimates derived from Timor Sea
and Indian Ocean studies. While this would favor the case C throughflow
of 6.7 Sv, with zero mean along channel flow at the sea surface
this may not be the only explanation. Perhaps we are seeing a
throughflow interannual (ENSO) signal (noting that the JADE Timor
Passage values were obtained during an El Niño period)?
Alternatively, might some of the Makassar transport pass back
to the Pacific Ocean to the east of Sulawesi? Comparison of the
MAK mooring results with: 1996-98 JADE mooring data near Timor
(Molcard and Fieux); Lesser Sunda Island shallow pressure gauge
array (Janet Sprintall); and data from the Arlindo mooring in
Lifamatola Passage (Fig. 1) to be recovered
in November 1998, may help resolve this issue.

Acknowledgment: The research is funded by NSF:
OCE 95-29648 and the Office
of Naval Research: N00014-98-1-0270. Gratitude and appreciation
is extended to Dr. Indroyono Soesilo and to Basri M. Ganie of
BPPT for arranging for the joint program and the ship time aboard
Baruna Jaya IV, to Gani Ilahude of LIPI for all that he has done
to promote the Arlindo project, and to Captain Handoko and his
fine staff aboard the Baruna Jaya IV. And finally we thank Baldeo
Singh of UNOCAL for the recovery of MAK-1 mooring in July 1998.